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Linzor Volcanic Chain, N. Chile: Tracking the Influence Of Journal of Volcanology and Geothermal Research 341 (2017) 172–186 Contents lists available at ScienceDirect Journal of Volcanology and Geothermal Research journal homepage: www.elsevier.com/locate/jvolgeores Sr- and Nd- isotope variations along the Pleistocene San Pedro – Linzor volcanic chain, N. Chile: Tracking the influence of the upper crustal Altiplano-Puna Magma Body Benigno Godoy a,⁎,GerhardWörnerb,PetrusLeRouxc, Shanaka de Silva d, Miguel Ángel Parada a, Shoji Kojima e, Osvaldo González-Maurel f, Diego Morata a, Edmundo Polanco g,1, Paula Martínez a,2 a Centro de Excelencia en Geotermia de los Andes (CEGA), Departamento de Geología, Facultad de Ciencas Físicas y Matemáticas, Universidad de Chile, Plaza Ercilla 803, Santiago, Chile b Abteilung Geochemie, GZG, Göttingen Universität, Goldschmidtstraße 1, Göttingen 37077, Germany c Department of Geological Sciences, University of Cape Town, Rondebosch 7701, South Africa d College of Earth, Ocean, and Atmospheric Sciences, Oregon State University, Corvallis, OR 97331, USA e Departamento de Ciencias Geológicas, Universidad Católica del Norte, Avenida Angamos 0610, Antofagasta, Chile f Programa de Doctorado en Ciencias, Mención Geología. Departamento de Ciencias Geólogicas, Universidad Católica del Norte, Avenida Angamos 0610, Antofagasta, Chile g Energía Andina S.A. Cerro El Plomo 5630, Las Condes, Santiago, Chile article info abstract Article history: Subduction-related magmas that erupted in the Central Andes during the past 10 Ma are strongly affected by Received 13 January 2017 crustal assimilation as revealed by an increase in 87Sr/86Sr isotope ratios with time that in turn are correlated Received in revised form 29 May 2017 with increased crustal thickening during the Andean orogeny. However, contamination is not uniform and can Accepted 29 May 2017 be strongly influenced locally by crustal composition, structure and thermal condition. This appears to be the Available online 31 May 2017 case along the NW-SE San Pedro - Linzor volcanic chain (SPLVC) in northern Chile, which straddles the boundary of a major zone of partial melt, the Altiplano_Puna Magma Body (APMB). Herein we report 40Ar/39Ar ages, com- Keywords: fl San Pedro – Linzor volcanic chain (SPLVC) positional and isotope data on lavas from the SPLVC that track the in uence of this zone of partial melting on Altiplano-Puna Magma Body (APMB) erupted lavas with geochronological and geochemical data. Ages reported here indicate that SPLVC has evolved Isotopic shift in the last 2 M.y., similar to other volcanoes of the Western Cordillera (e.g. Lascar, Uturuncu, Putana). 87Sr/86Sr Geochronology ratios increase systematically along the chain from a minimum value of 0.7057 in San Pedro dacites to a maxi- mum of 0.7093–0.7095 for the Toconce and Cerro de Leon dacites in the SE. These changes are interpreted to re- flect the increasing interaction of SPLVC parental magmas with partial melt within the APMB eastwards across the chain. The 87Sr/86Sr ratio and an antithetic trend in 143Nd/144Nd is therefore a proxy for the contribution of melt from the APMB beneath this volcanic chain. Similar 87Sr/86Sr increases and 143Nd/144Nd decreases are observed in other transects crossing the boundary of the APMB. Such trends can be recognized from NW to SE between Aucanquilcha, Ollagüe, and Uturuncu volca- noes, and from Lascar volcano to the N-S-trending Putana-Sairecabur-Licancabur volcanic chain to the north. We interpret these isotopic trends as reflecting different degrees of interaction of mafic parental melts with the APMB. High 87Sr/86Sr, and low 143Nd/144Nd reveal zones where the APMB is thicker (~20 km) and more melt-dominated (~25% vol. partial melt) while lower 87Sr/86Sr, and higher 143Nd/144Nd reveal thinner marginal zones of the APMB where lower contents of partial melt (b10% vol) involves reduced interactions. The lowest Sr- isotope ratios, and higher Nd-isotope ratios (where available) occur in magmas erupted outside the APMB (e.g. San Pedro, Lascar and Aucanquilcha volcanoes), indicating a diminished influence of crustal partial melts on pa- rental mafic magmas. These geochemical parameters provide a useful tracer for the extent and significance of crustal partial melt bodies in magma genesis in the Central Andes. © 2017 Elsevier B.V. All rights reserved. 1. Introduction ⁎ Corresponding author. E-mail address: [email protected] (B. Godoy). While it is known that most magma at subduction zones is generat- 1 Present address: Servicio Nacional de Geología y Minería, Avenida Santa María 0104, ed by flux melting in the asthenospheric wedge (Tatsumi et al., 1983; Providencia, Santiago, Chile. 2 Present address: Advanced Mining Technology Center, Avenida Tupper 2007, Grove et al., 2012), in continental magmatic arcs, the role of the crust Santiago, Chile. in controlling the evolution of even the most maficmagmasisclear http://dx.doi.org/10.1016/j.jvolgeores.2017.05.030 0377-0273/© 2017 Elsevier B.V. All rights reserved. B. Godoy et al. / Journal of Volcanology and Geothermal Research 341 (2017) 172–186 173 (e.g. Davidson et al., 1990). This is most obvious in arcs built on thick A dominant feature of the Neogene history of the Central Andes is continental crust such as the Central Volcanic Zone (CVZ) of the one the most extensive ignimbrite plateaus on Earth, the Neogene Cen- Andes. Arc migration and crustal thickening to 70 km in the Central tral Andean Ignimbrite Province (Coira et al., 1982; de Silva and Francis, Andes are well documented (e.g. Scheuber and Giese, 1999; Scheuber 1991; Trumbull et al., 2006; Salisbury et al., 2011; Freymuth et al., 2015; and Reutter, 1992, Beck et al., 1996; Allmendinger et al., 1997; Kay Brandmeier and Wörner, 2016). The most intense activity produced the and Mpodozis, 2001; Oncken et al., 2006; Hartley et al., 2007; Kley et Altiplano-Puna Volcanic Complex (APVC, de Silva, 1989), a volcano-tec- al., 1999; Kley and Monaldi, 1998) and have been related to the system- tonic province in the Central Andes occupying the high plateau between atic spatio-temporal changes in the geochemical and isotopic composi- 21° and 24°S (Fig. 1). The area of the APVC coincides with the surface tion of erupted lavas during the last 26 M.y. (e.g. Haschke, 2002; Kay et projection of a low-velocity zone, interpreted as a partially-molten al., 2005; Haschke et al., 2006; Mamani et al., 2008, 2010). Volcanic body within the upper crust (~15 to 30 km), the so-called “Altiplano- rocks of earlier stages of Central Andean evolution traversed thin crust Puna Magma Body” (AMPB; Chmielowski et al., 1999; Zandt et al., and are consistently low in Sr/Y, La/Yb, and Sm/Yb ratios, whereas pro- 2003; Ward et al., 2014)(Fig. 1). This body has also been recognized gressively younger magmatic products show increases in the maximum by electrical, gravity, and isostatic anomalies (Schilling et al., 1997; Sr/Y, La/Yb, and Sm/Yb ratios. These changes in the geochemical signa- Haberland and Rietbrock, 2001; Schilling and Partzsch, 2001; Brasse et ture of lavas were attributed to the increasing role of garnet as a stable al., 2002; Schnurr et al., 2007; Prezzi et al., 2009), and is interpreted as residual phase in magma processing within a progressively thicker Cen- an incrementally constructed, upper-crustal batholith (de Silva and tral Andean crust. This is in line with the more radiogenic signatures of Gosnold, 2007; Kern et al., 2016) atop an upper crustal MASH zone the magmatism with time that are attributed to increased crustal assim- (Burns et al., 2015; Ward et al., 2014). ilation (Rogers and Hawkesworth, 1989; Kay and Mpodozis, 2001; Tracking the influence of this partially molten upper crustal batho- Davidson et al., 1990; Haschke, 2002; Haschke et al., 2006; Mamani et lith on magma compositions in arc front volcanism is our aim in this al., 2008, 2010). study. The hypothesis is that crustal partial melts will be more Fig. 1. Global Multi-Resolution Topography image showing location of the volcanic structures (black stars) included in this study: Aucanquilcha (1) – Ollagüe (2) – Uturuncu (3) transect (Michelfelder et al., 2013); San Pedro (4) – Linzor (5) volcanic chain (SPLVC), including La Poruña scorica cone (6), and Paniri (7), Cerro del León (8) and Toconce (9) volcanoes (Godoy et al., 2014); Putana (10) – Sairecabur (11) – Licancabur (12) transect, including Purico-Chascón Volcanic Complex (13), and Lascar volcano (14). Dotted areas indicate distribution of Altiplano-Puna Volcanic Complex (APVC, thick) and surface projection of the Altiplano-Puna Magma Body (APMB, thin) (after Zandt et al., 2003). Dashed grey areas indicate extend of joint ambient noise-receiver function inversion S-velocity (Vs) models contours, at 15 km b.s.l., for velocities b3.2 km/s (Ward et al., 2014). Thick lined polygon indicates extend of geological map from Fig. 2. 174 B. Godoy et al. / Journal of Volcanology and Geothermal Research 341 (2017) 172–186 efficiently mixed and at higher proportions with parental mafic and Francis, 1986; Lazcano et al., 2012; López et al., 2012; Polanco et magmas and therefore have more leverage on the geochemical compo- al., 2012; Silva et al., 2012; López, 2014; Martínez, 2014; Silva, 2015; sition of the erupted lavas than solid crust. Here we use radiogenic iso- Lazcano, 2016). The ~100 ka Chillahuita dome and giant Chao dacitic topes and geochronological data to map the influence of the APMB. To coulée (Guest and Sanchez, 1969; de Silva et al., 1994; Tierney et al., this end we present new geochronological (40Ar/39Ar) and isotopic 2016) are also included in the chain (Fig. 2). Finally, the ~103 ka La (87Sr/86Sr and 143Nd/144Nd) data combined with a compilation of pub- Poruña basaltic-andesite scoria cone is the source of a 8 km long lava lished geochemical data from the NW-SE San Pedro – Linzor volcanic flow at the far NW end of the SPVC (O'Callaghan and Francis, 1986; chain (SPLVC) in N.
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